Beringia is the region spanning eastern Asia and northwestern North America that remained ice-free during the full glacial events of the Pleistocene. Numerous questions persist regarding the importance of this region in the evolution of northern faunas. Beringia has been implicated as both a high latitude refugium and as the crossroads (Bering Land Bridge) of the northern continents for boreal mammals. The Beringian Coevolution Project (BCP) is an international collaboration that has provided material to assess the pattern and timing of faunal exchange across the crossroads of the northern continents and the potential impact of past climatic events on differentiation. Mammals and associated parasite specimens have been collected and preserved from more than 200 field sites in eastern Russia, Alaska and northwestern Canada since 1999. Previously, fossils and taxonomic comparisons between Asia and North America mammals have shed light on these events. Molecular phylogenetics based on BCP specimens is now being used to trace the history of faunal exchange and diversification. We have found substantial phylogeographic structure in the Arctic and in Beringia in mustelid carnivores, arvicoline rodents, arctic hares and soricine shrews, including spatially concordant clades and contact zones across taxa that correspond to the edges of Beringia. Among the tapeworms of these mammalian hosts, new perspectives on diversity have also been developed. Arostrilepis horrida (Hymenolepididae) was considered to represent a single widespread and morphologically variable species occurring in a diversity of voles and lemmings in eastern and western Beringia and more broadly across the Holarctic region. The BCP has demonstrated a complex of at least 10 species that are poorly differentiated morphologically. The diversity of Paranoplocephala spp. and Anolocephaloides spp. (Anoplocephalidae) in Beringia included relatively few widespread and morphologically variable species in arvicolines. BCP collections have changed this perspective, allowing the recognition of a series of highly endemic species of Paranoplocephala that demonstrate very narrow host specificity, and additional species complexes among arvicolines. Thus, extensive, previously unrecognized, diversity for tapeworms of 2 major families characterizes the Beringian fauna. By elucidating evolutionary relationships and phylogeographic variation among populations, species and assemblages, refined views of the sequence and timing of biotic expansion, geographic colonization and impact of episodic climate change have been developed for Beringia. Ultimately, Beringia was a determining factor in the structure and biogeography of terrestrial faunas across the Nearctic and Neotropical regions during the Pliocene and Quaternary.
","language":"English","publisher":"Mammal Society of Japan","doi":"10.3106/1348-6160(2005)30[33:BIEADO]2.0.CO;2","usgsCitation":"Cook, J.A., Hoberg, E.P., Koehler, A., Henttonen, H., Wickstrom, L., Haukisalmi, V., Galbreath, K.E., Chernyavski, F., Dokuchaev, N., Lahzuhtkin, A., MacDonald, S.O., Hope, A.G., Waltari, E., Runck, A., Veitch, A., Jenkins, E., Kutz, S., and Eckerlin, R., 2005, Beringia: Intercontinental exchange and diversification of high latitude mammals and their parasites during the Pliocene and Quaternary: Mammal Study, v. 30, no. sp1, p. S33-S44, https://doi.org/10.3106/1348-6160(2005)30[33:BIEADO]2.0.CO;2.","productDescription":"12 p.","startPage":"S33","endPage":"S44","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"links":[{"id":494170,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.3106/1348-6160(2005)30[33:bieado]2.0.co;2","text":"Publisher Index Page"},{"id":336987,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada, Russia, United States","otherGeospatial":"Berengia","volume":"30","issue":"sp1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"58bfd4ffe4b014cc3a3ba538","contributors":{"authors":[{"text":"Cook, Joseph A.","contributorId":70318,"corporation":false,"usgs":true,"family":"Cook","given":"Joseph","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":681110,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hoberg, Eric P.","contributorId":102448,"corporation":false,"usgs":false,"family":"Hoberg","given":"Eric","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":681111,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Koehler, Anson V.","contributorId":73740,"corporation":false,"usgs":true,"family":"Koehler","given":"Anson V.","affiliations":[],"preferred":false,"id":681112,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Henttonen, Heikki","contributorId":187632,"corporation":false,"usgs":false,"family":"Henttonen","given":"Heikki","email":"","affiliations":[],"preferred":false,"id":681113,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Wickstrom, Lotta","contributorId":187633,"corporation":false,"usgs":false,"family":"Wickstrom","given":"Lotta","email":"","affiliations":[],"preferred":false,"id":681114,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Haukisalmi, Voitto","contributorId":187634,"corporation":false,"usgs":false,"family":"Haukisalmi","given":"Voitto","email":"","affiliations":[],"preferred":false,"id":681115,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Galbreath, Kurt E.","contributorId":48867,"corporation":false,"usgs":true,"family":"Galbreath","given":"Kurt","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":681116,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Chernyavski, Felix","contributorId":187635,"corporation":false,"usgs":false,"family":"Chernyavski","given":"Felix","email":"","affiliations":[],"preferred":false,"id":681117,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Dokuchaev, Nikolai","contributorId":187636,"corporation":false,"usgs":false,"family":"Dokuchaev","given":"Nikolai","email":"","affiliations":[],"preferred":false,"id":681118,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Lahzuhtkin, Anatoli","contributorId":187637,"corporation":false,"usgs":false,"family":"Lahzuhtkin","given":"Anatoli","email":"","affiliations":[],"preferred":false,"id":681119,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"MacDonald, Stephen O.","contributorId":187638,"corporation":false,"usgs":false,"family":"MacDonald","given":"Stephen","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":681120,"contributorType":{"id":1,"text":"Authors"},"rank":11},{"text":"Hope, Andrew G. 0000-0003-3814-2891 ahope@usgs.gov","orcid":"https://orcid.org/0000-0003-3814-2891","contributorId":4309,"corporation":false,"usgs":true,"family":"Hope","given":"Andrew","email":"ahope@usgs.gov","middleInitial":"G.","affiliations":[{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"preferred":true,"id":681121,"contributorType":{"id":1,"text":"Authors"},"rank":12},{"text":"Waltari, Eric","contributorId":105946,"corporation":false,"usgs":false,"family":"Waltari","given":"Eric","affiliations":[],"preferred":false,"id":681122,"contributorType":{"id":1,"text":"Authors"},"rank":13},{"text":"Runck, Amy","contributorId":187640,"corporation":false,"usgs":false,"family":"Runck","given":"Amy","email":"","affiliations":[],"preferred":false,"id":681123,"contributorType":{"id":1,"text":"Authors"},"rank":14},{"text":"Veitch, Alasdair","contributorId":187641,"corporation":false,"usgs":false,"family":"Veitch","given":"Alasdair","email":"","affiliations":[],"preferred":false,"id":681124,"contributorType":{"id":1,"text":"Authors"},"rank":15},{"text":"Jenkins, Emily","contributorId":187643,"corporation":false,"usgs":false,"family":"Jenkins","given":"Emily","email":"","affiliations":[],"preferred":false,"id":681125,"contributorType":{"id":1,"text":"Authors"},"rank":16},{"text":"Kutz, Susan","contributorId":187644,"corporation":false,"usgs":false,"family":"Kutz","given":"Susan","affiliations":[],"preferred":false,"id":681126,"contributorType":{"id":1,"text":"Authors"},"rank":17},{"text":"Eckerlin, Ralph P.","contributorId":17087,"corporation":false,"usgs":true,"family":"Eckerlin","given":"Ralph P.","affiliations":[],"preferred":false,"id":681127,"contributorType":{"id":1,"text":"Authors"},"rank":18}]}} ,{"id":70507,"text":"sim2884 - 2005 - Precambrian crystalline basement map of Idaho: An interpretation of aeromagnetic anomalies","interactions":[],"lastModifiedDate":"2022-12-14T21:20:58.248532","indexId":"sim2884","displayToPublicDate":"2005-05-03T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":333,"text":"Scientific Investigations Map","code":"SIM","onlineIssn":"2329-132X","printIssn":"2329-1311","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2884","title":"Precambrian crystalline basement map of Idaho: An interpretation of aeromagnetic anomalies","docAbstract":"Idaho lies within the northern sector of the U.S. Cordillera astride the \r\n boundary between the Proterozoic continent (Laurentia) to the east and \r\n the Permian to Jurassic accreted terranes to the west. The continental \r\n basement is mostly covered by relatively undeformed Mesoproterozoic \r\n metasedimentary rocks and intruded or covered by Phanerozoic igneous \r\n rocks; accordingly, knowledge of the basement geology is poorly \r\n constrained. Incremental knowledge gained since the pioneering studies \r\n by W. Lindgren, C.P. Ross, A.L. Anderson, A. Hietanen, and others during \r\n the early- and mid-1900's has greatly advanced our understanding of the \r\n general geology of Idaho. However, knowledge of the basement geology \r\n remains relatively poor, partly because of the remoteness of much of the \r\n region plus the lack of a stimulus to decipher the complex assemblage of \r\n high-grade gneisses and migmatite of central Idaho. The availability of \r\n an updated aeromagnetic anomaly map of Idaho (North American Magnetic \r\n Anomaly Group, 2002) provides a means to determine the regional \r\n Precambrian geologic framework of the State. The combined geologic and \r\n aeromagnetic data permit identification of previously unrecognized \r\n crystalline basement terranes, assigned to Archean and Paleoproterozoic \r\n ages, and the delineation of major shear zones, which are expressed in \r\n the aeromagnetic data as linear negative anomalies (Finn and Sims, \r\n 2004). Limited geochronologic data on exposed crystalline basement \r\n aided by isotopic studies of zircon inheritance, particularly Bickford \r\n and others (1981) and Mueller and others (1995), provide much of the \r\n geologic background for our interpretation of the basement geology. In \r\n northwestern United States, inhomogeneities in the basement inherited \r\n from Precambrian tectogenesis controlled many large-scale tectonic \r\n features that developed during the Phanerozoic. Two basement \r\n structures, in particular, provided zones of weakness that were \r\n repeatedly rejuvenated: (1) northeast-trending ductile shear zones \r\n developed on the northwest margin of the Archean Wyoming province during \r\n the Paleoproterozoic Trans-Montana orogeny (Sims and others, 2004), and \r\n (2) northwest-trending intra-continental faults of the Mesoproterozoic \r\n Trans-Rocky Mountain strike-slip fault system (Sims, unpub. data, 2003). \r\n In this report, geologic ages are reported in millions of years (Ma) and \r\n generalized ages are given in billions of years (Ga). The subdivision \r\n of Precambrian rocks used herein is the time classification recommended \r\n by the International Union of Geological Sciences (Plumb, 1991).","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sim2884","usgsCitation":"Sims, P., Lund, K., and Anderson, E., 2005, Precambrian crystalline basement map of Idaho: An interpretation of aeromagnetic anomalies (Version 1.0): U.S. Geological Survey Scientific Investigations Map 2884, Report: 21 p.; 1 Plate: 56.50 × 36.50 inches; Metadata: Downloads Directory, https://doi.org/10.3133/sim2884.","productDescription":"Report: 21 p.; 1 Plate: 56.50 × 36.50 inches; Metadata: Downloads Directory","costCenters":[{"id":171,"text":"Central Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":187804,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":110559,"rank":2,"type":{"id":36,"text":"NGMDB Index 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\"}}]}","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac7e4b07f02db67b2ac","contributors":{"authors":[{"text":"Sims, P.K.","contributorId":30191,"corporation":false,"usgs":true,"family":"Sims","given":"P.K.","email":"","affiliations":[],"preferred":false,"id":282558,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lund, Karen 0000-0002-4249-3582 klund@usgs.gov","orcid":"https://orcid.org/0000-0002-4249-3582","contributorId":1235,"corporation":false,"usgs":true,"family":"Lund","given":"Karen","email":"klund@usgs.gov","affiliations":[{"id":171,"text":"Central Mineral and Environmental Resources Science Center","active":true,"usgs":true},{"id":387,"text":"Mineral Resources Program","active":true,"usgs":true}],"preferred":true,"id":282557,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Anderson, E.","contributorId":100078,"corporation":false,"usgs":true,"family":"Anderson","given":"E.","affiliations":[],"preferred":false,"id":282559,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70238534,"text":"70238534 - 2005 - Radioisotopic and biostratigraphic age relations in the Coast Range Ophiolite, northern California: Implications for the tectonic evolution of the Western Cordillera","interactions":[],"lastModifiedDate":"2022-11-28T19:06:26.49107","indexId":"70238534","displayToPublicDate":"2005-05-01T12:52:19","publicationYear":"2005","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Radioisotopic and biostratigraphic age relations in the Coast Range Ophiolite, northern California: Implications for the tectonic evolution of the Western Cordillera","docAbstract":"The Coast Range ophiolite (CRO) in northern California includes two distinct remnants. The Elder Creek ophiolite is a classic suprasubduction zone ophiolite with three sequential plutonic suites (layered gabbro, wehrlit-pyroxenite, quartz diorite), a mafic to felsic dike complex, and mafic-felsic volcanic rocks; the entire suite is cut by late mid-oceanic-ridge basalt (MORB) dikes and overlain by ophiolitic breccia. The Stonyford volcanic complex (SFVC) comprises three volcanic series with intercalated chert horizons that form a submarine volcano enclosed in sheared serpentinite. Structurally below this seamount are mélange blocks of CRO similar to Elder Creek.
U/Pb zircon ages from plagiogranite and quartz diorites at Elder Creek range in age from 165 Ma to 172 Ma. U/Pb zircon ages obtained from CRO mélange blocks below the SFVC are similar (166–172 Ma). 40Ar-39Ar ages of alkali basalt glass in the upper SFVC are all younger at ≈164 Ma. Radiolarians extracted from chert lenses intercalated with basalt in the SFVC indicate that the sedimentary strata range in age from Bathonian (Unitary Association Zone 6–6 of Baumgartner et al., 1995a) near the base of the complex to late Callovian to early Kimmeridgian (Unitary Association Zones 8–10) in the upper part. The SFVC sedimentary record preserves evidence of a major faunal change wherein relatively small sized, polytaxic radiolarian faunas were replaced by very robust, oligo-taxic, nassellarian-dominated faunas that included Praeparvicingula spp.
We suggest that CRO formation began after the early Middle Jurassic (172–180 Ma) collision of an exotic or fringing arc with North America and initiation of a new or reconfigured east-dipping subduction zone. The data show that the CRO formed prior to the Late Jurassic Nevadan orogeny, probably by rapid forearc extension above a nascent subduction zone. We infer that CRO spreading ended with the collision of an oceanic spreading center ca. 164 Ma, coincident with the oldest high-grade blocks in the structurally underlying Franciscan assemblage. We further suggest that the “classic” Nevadan orogeny represents a response to spreading center collision, with shallow subduction of young lithosphere causing the initial compressional deformation and with a subsequent change in North American plate motion to rapid northward drift (J2 cusp) causing sinistral transpression and transtension in the Sierra foothills. These data are not consistent with models for Late Jurassic arc collision in the Sierra foothills or a backarc origin for the CRO.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/B25443.1","usgsCitation":"Shervais, J., Murchey, B.L., Kimbrough, D.L., Renne, P.R., and Hanan, B., 2005, Radioisotopic and biostratigraphic age relations in the Coast Range Ophiolite, northern California: Implications for the tectonic evolution of the Western Cordillera: GSA Bulletin, v. 117, no. 5-6, p. 633-653, https://doi.org/10.1130/B25443.1.","productDescription":"21 p.","startPage":"633","endPage":"653","costCenters":[],"links":[{"id":409741,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Coast Range","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -122.73012721058606,\n 40.36957762617669\n ],\n [\n -123.95470669447536,\n 40.192835793178716\n ],\n [\n -123.71751337101955,\n 39.91839653077014\n ],\n [\n -123.32586858112697,\n 39.481255320560564\n ],\n [\n -122.5536112489444,\n 39.591862843388554\n ],\n [\n -122.49845001093107,\n 39.753202807470814\n ],\n [\n -122.54809512514294,\n 39.83373143404421\n ],\n [\n -122.53154675373919,\n 39.994505732745694\n ],\n [\n -122.68048209637419,\n 40.20547553087849\n ],\n [\n -122.73012721058606,\n 40.36957762617669\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"117","issue":"5-6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Shervais, John W.","contributorId":237914,"corporation":false,"usgs":false,"family":"Shervais","given":"John W.","affiliations":[{"id":6682,"text":"Utah State University","active":true,"usgs":false}],"preferred":false,"id":857761,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Murchey, Benita L. bmurchey@usgs.gov","contributorId":504,"corporation":false,"usgs":true,"family":"Murchey","given":"Benita","email":"bmurchey@usgs.gov","middleInitial":"L.","affiliations":[],"preferred":true,"id":857762,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kimbrough, David L.","contributorId":211569,"corporation":false,"usgs":false,"family":"Kimbrough","given":"David","email":"","middleInitial":"L.","affiliations":[{"id":6608,"text":"San Diego State University","active":true,"usgs":false}],"preferred":false,"id":857763,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Renne, Paul R. 0000-0003-1769-5235","orcid":"https://orcid.org/0000-0003-1769-5235","contributorId":229577,"corporation":false,"usgs":false,"family":"Renne","given":"Paul","email":"","middleInitial":"R.","affiliations":[{"id":37390,"text":"Department of Earth and Planetary Science, University of California, Berkeley","active":true,"usgs":false}],"preferred":false,"id":857764,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Hanan, Barry","contributorId":299415,"corporation":false,"usgs":false,"family":"Hanan","given":"Barry","email":"","affiliations":[{"id":6608,"text":"San Diego State University","active":true,"usgs":false}],"preferred":false,"id":857765,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70466,"text":"sir20045146 - 2005 - Chemical characteristics of ground-water discharge along the south rim of Grand Canyon in Grand Canyon National Park, Arizona, 2000-2001","interactions":[],"lastModifiedDate":"2020-02-04T09:14:13","indexId":"sir20045146","displayToPublicDate":"2005-04-25T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2004-5146","title":"Chemical characteristics of ground-water discharge along the south rim of Grand Canyon in Grand Canyon National Park, Arizona, 2000-2001","docAbstract":"Springs flowing from the south rim of Grand Canyon are an important resource of Grand Canyon National Park, offering refuge to endemic and exotic terrestrial wildlife species and maintaining riparian areas. Population growth on the Coconino Plateau has increased the demand for additional development of ground-water resources, and such development could reduce spring discharge and affect the sustainability of riparian areas within the park. In addition, springs are an important source of drinking water for hikers and are culturally and economically important to Native Americans living in the region.\r\n\r\n\r\nWater samples were collected from May 2000 to September 2001 from 20 spring and creek sites that discharge water from the Redwall-Muav Limestone aquifer along the south rim of Grand Canyon. Sample collection sites were described and samples were analyzed for major ions, nutrients, trace elements, radioactivity, and selected isotopes, and potential sources of ground-water flow to the springs. Rock samples representing the major stratigraphic units of Grand Canyon were collected near the Bright Angel Fault and analyzed for mineralogy, strontium-87/strontium-86, and \r\ncarbon-13/carbon-12.\r\n\r\n\r\nThe chemical composition of water samples collected from a given spring did not vary appreciably over the course of the study. Although water at each spring had a temporally constant composition, the composition was chemically distinct from that of every other spring sampled, indicating spatial variability in the ground-water composition. Most samples had a calcium magnesium bicarbonate composition; a few had a substantial sulfate component. Concentrations of arsenic, nitrate, selenium, uranium, and gross alpha approached or exceeded U.S. Environmental Protection Agency Maximum Contaminant Levels in water discharging from some springs. Oxygen and hydrogen isotopic compositions varied little among samples, and for most sites the isotopic data plot close to the global meteoric water line or below the local meteoric water line. Isotopic enrichment indicates fractionation due to evaporation occurs at some sites. The evaporative process may occur prior to recharge or post-discharge. Flow paths are differentiated between the eastern part of the study area where strontium-87/strontium-86 values for water from springs and creeks are more radiogenic than strontium-87/strontium-86 values for water that discharges from sites farther west. Tritium and carbon isotope analyses indicate that residence time of ground-water discharge from springs and creeks ranges from less than 50 years to about 3,400 years. Water with a residence time of less than 50 years is absent at several sites. Discharge of most springs and creeks is a mixture of younger and older waters.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20045146","usgsCitation":"Monroe, S.A., Antweiler, R.C., Hart, R.J., Taylor, H.E., Truini, M., Rihs, J.R., and Felger, T.J., 2005, Chemical characteristics of ground-water discharge along the south rim of Grand Canyon in Grand Canyon National Park, Arizona, 2000-2001: U.S. Geological Survey Scientific Investigations Report 2004-5146, 71 p., https://doi.org/10.3133/sir20045146.","productDescription":"71 p.","costCenters":[{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":188774,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6428,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/sir2004-5146/","linkFileType":{"id":5,"text":"html"}}],"scale":"24000","country":"United States","state":"Arizona","otherGeospatial":"Grand Canyon National Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -112.587890625,\n 35.96689214303232\n ],\n [\n -111.84356689453125,\n 35.96689214303232\n ],\n [\n -111.84356689453125,\n 36.48093224547937\n ],\n [\n -112.587890625,\n 36.48093224547937\n ],\n [\n -112.587890625,\n 35.96689214303232\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e0e4b07f02db5e4742","contributors":{"authors":[{"text":"Monroe, Stephen A.","contributorId":103313,"corporation":false,"usgs":true,"family":"Monroe","given":"Stephen","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":282495,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Antweiler, Ronald C. 0000-0001-5652-6034 antweil@usgs.gov","orcid":"https://orcid.org/0000-0001-5652-6034","contributorId":1481,"corporation":false,"usgs":true,"family":"Antweiler","given":"Ronald","email":"antweil@usgs.gov","middleInitial":"C.","affiliations":[{"id":5044,"text":"National Research Program - Central Branch","active":true,"usgs":true}],"preferred":true,"id":282492,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hart, Robert J. bhart@usgs.gov","contributorId":598,"corporation":false,"usgs":true,"family":"Hart","given":"Robert","email":"bhart@usgs.gov","middleInitial":"J.","affiliations":[{"id":128,"text":"Arizona Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282489,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Taylor, Howard E. hetaylor@usgs.gov","contributorId":1551,"corporation":false,"usgs":true,"family":"Taylor","given":"Howard","email":"hetaylor@usgs.gov","middleInitial":"E.","affiliations":[{"id":5044,"text":"National Research Program - Central Branch","active":true,"usgs":true}],"preferred":true,"id":282493,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Truini, Margot mtruini@usgs.gov","contributorId":599,"corporation":false,"usgs":true,"family":"Truini","given":"Margot","email":"mtruini@usgs.gov","affiliations":[{"id":128,"text":"Arizona Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282490,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Rihs, John R.","contributorId":57954,"corporation":false,"usgs":true,"family":"Rihs","given":"John","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":282494,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Felger, Tracey J. 0000-0003-0841-4235 tfelger@usgs.gov","orcid":"https://orcid.org/0000-0003-0841-4235","contributorId":1117,"corporation":false,"usgs":true,"family":"Felger","given":"Tracey","email":"tfelger@usgs.gov","middleInitial":"J.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":282491,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":70469,"text":"sir20055068 - 2005 - Water-quality, phytoplankton, and trophic-status characteristics of Big Base and Little Base lakes, Little Rock Air Force Base, Arkansas, 2003-2004","interactions":[],"lastModifiedDate":"2012-02-02T00:13:32","indexId":"sir20055068","displayToPublicDate":"2005-04-25T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2005-5068","title":"Water-quality, phytoplankton, and trophic-status characteristics of Big Base and Little Base lakes, Little Rock Air Force Base, Arkansas, 2003-2004","docAbstract":"Little Rock Air Force Base is the largest C-130 base in the Air Force and is the only C-130 training base in the Department of Defense. Little Rock Air Force Base is located in central Arkansas near the eastern edge of the Ouachita Mountains, near the Mississippi Alluvial Plain, and within the Arkansas Valley Ecoregion. Habitats include upland pine forests, upland deciduous forest, broad-leaved deciduous swamps, and two small freshwater lakes?Big Base Lake and Little Base Lake. Big Base and Little Base Lakes are used primarily for recreational fishing by base personnel and the civilian public. Under normal (rainfall) conditions, Big Base Lake has a surface area of approximately 39 acres while surface area of Little Base Lake is approximately 1 acre. \r\n\r\nLittle Rock Air Force Base personnel are responsible for managing the fishery in these two lakes and since 1999 have started a nutrient enhancement program that involves sporadically adding fertilizer to Big Base Lake. As a means of determining the relations between water quality and primary production, Little Rock Air Force Base personnel have a need for biological (phytoplankton density), chemical (dissolved-oxygen and nutrient concentrations), and physical (water temperature and light transparency) data. To address these monitoring needs, the U.S. Geological Survey in cooperation with Little Rock Air Force Base, conducted a study to collect and analyze biological, chemical, and physical data. The U.S. Geological Survey sampled water quality in Big Base Lake and Little Base Lake on nine occasions from July 2003 through June 2004. Because of the difference in size, two sampling sites were established on Big Base Lake, while only one site was established on Little Base Lake. \r\n\r\nLake profile data for Big Base Lake indicate that low dissolved- oxygen concentrations in the hypolimnion probably constrain most fish species to the upper 5-6 feet of depth during the summer stratification period. Dissolved-oxygen concentrations in Big Base Lake below a depth of 6 feet generally were less than 3 milligrams per liter for summer months that were sampled in 2003 and 2004. \r\n\r\nSome evidence indicates that phosphorus was limiting primary production during the sampling period. Dissolved nitrogen constituents frequently were detected in water samples (indicating availability) but dissolved phosphorus constituents-orthophosphorus and dissolved phosphorus-were not detected in any samples collected at the two lakes. The absence of dissolved phosphorus constituents and presence of total phosphorus indicates that all phosphorus was bound to suspended material (sediment particles and living organisms). Nitrogen:phosphorus ratios on most sampling occasions tended to be slightly higher than 16:1, which can be interpreted as further indication that phosphorus could be limiting primary production to some extent. \r\n\r\nAn alkalinity of 20 milligrams per liter of calcium carbonate or higher is recommended to optimize nutrient availability and buffering capacity in recreational fishing lakes and ponds. Median values for water samples collected at the three sites ranged from 12-13 milligrams per liter of calcium carbonate. Alkalinities ranged from 9-60 milligrams per liter of calcium carbonate, but 13 of 17 samples collected at the deepest site had alkalinities less than 20 milligrams per liter of calcium carbonate. \r\n\r\nResults of three trophic-state indices, and a general trophic classification, as well as abundant green algae and large growths of blue-green algae indicate that Big Base Lake may be eutrophic. Trophic-state index values calculated using total phosphorus, chlorophyll a, and Secchi disc measurements from both lakes generally exceeded criteria at which lakes are considered to be eutrophic. A second method of determining lake trophic status-the general trophic classification-categorized the three sampling sites as mesotrophic or eutrophic. Green algae were found to be in abundance throughout mos","language":"ENGLISH","doi":"10.3133/sir20055068","usgsCitation":"Justus, B., 2005, Water-quality, phytoplankton, and trophic-status characteristics of Big Base and Little Base lakes, Little Rock Air Force Base, Arkansas, 2003-2004: U.S. Geological Survey Scientific Investigations Report 2005-5068, 37 p., https://doi.org/10.3133/sir20055068.","productDescription":"37 p.","costCenters":[],"links":[{"id":6431,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/sir2005-5068/","linkFileType":{"id":5,"text":"html"}},{"id":188859,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"scale":"24000","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e3e4b07f02db5e5191","contributors":{"authors":[{"text":"Justus, B. G.","contributorId":49825,"corporation":false,"usgs":true,"family":"Justus","given":"B. G.","affiliations":[],"preferred":false,"id":282499,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70401,"text":"sir20055038 - 2005 - Comparison of methods for estimating ground-water recharge and base flow at a small watershed underlain by fractured bedrock in the Eastern United States","interactions":[],"lastModifiedDate":"2017-07-10T10:47:56","indexId":"sir20055038","displayToPublicDate":"2005-04-18T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2005-5038","title":"Comparison of methods for estimating ground-water recharge and base flow at a small watershed underlain by fractured bedrock in the Eastern United States","docAbstract":"This study by the U.S. Geological Survey (USGS), in cooperation with the Agricultural Research Service (ARS), U.S. Department of Agriculture, compared multiple methods for estimating ground-water recharge and base flow (as a proxy for recharge) at sites in east-central Pennsylvania underlain by fractured bedrock and representative of a humid-continental climate. This study was one of several within the USGS Ground-Water Resources Program designed to provide an improved understanding of methods for estimating recharge in the eastern United States.\r\n\r\nRecharge was estimated on a monthly and annual basis using four methods?(1) unsaturated-zone drainage collected in gravity lysimeters, (2) daily water balance, (3) water-table fluctuations in wells, and (4) equations of Rorabaugh. Base flow was estimated by streamflow-hydrograph separation using the computer programs PART and HYSEP. Estimates of recharge and base flow were compared for an 8-year period (1994-2001) coinciding with operation of the gravity lysimeters at an experimental recharge site (Masser Recharge Site) and a longer 34-year period (1968-2001), for which climate and streamflow data were available on a 2.8-square-mile watershed (WE-38 watershed). \r\n\r\nEstimates of mean-annual recharge at the Masser Recharge Site and WE-38 watershed for 1994-2001 ranged from 9.9 to 14.0 inches (24 to 33 percent of precipitation). Recharge, in inches, from the various methods was: unsaturated-zone drainage, 12.2; daily water balance, 12.3; Rorabaugh equations with PULSE, 10.2, or RORA, 14.0; and water-table fluctuations, 9.9. Mean-annual base flow from streamflow-hydrograph separation ranged from 9.0 to 11.6 inches (21-28 percent of precipitation). Base flow, in inches, from the various methods was: PART, 10.7; HYSEP Local Minimum, 9.0; HYSEP Sliding Interval, 11.5; and HYSEP Fixed Interval, 11.6.\r\n\r\nEstimating recharge from multiple methods is useful, but the inherent differences of the methods must be considered when comparing results. For example, although unsaturated-zone drainage from the gravity lysimeters provided the most direct measure of potential recharge, it does not incorporate spatial variability that is contained in watershed-wide estimates of net recharge from the Rorabaugh equations or base flow from streamflow-hydrograph separation. This study showed that water-level fluctuations, in particular, should be used with caution to estimate recharge in low-storage fractured-rock aquifers because of the variability of water-level response among wells and sensitivity of recharge to small errors in estimating specific yield. To bracket the largest range of plausible recharge, results from this study indicate that recharge derived from RORA should be compared with base flow from the Local-Minimum version of HYSEP.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20055038","usgsCitation":"Risser, D.W., Gburek, W.J., and Folmar, G.J., 2005, Comparison of methods for estimating ground-water recharge and base flow at a small watershed underlain by fractured bedrock in the Eastern United States: U.S. Geological Survey Scientific Investigations Report 2005-5038, 37 p., https://doi.org/10.3133/sir20055038.","productDescription":"37 p.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":6961,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/sir2005-5038/","linkFileType":{"id":5,"text":"html"}},{"id":186010,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -77.11666666666666,41.11666666666667 ], [ -77.11666666666666,41.25 ], [ -76.83333333333333,41.25 ], [ -76.83333333333333,41.11666666666667 ], [ -77.11666666666666,41.11666666666667 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b23e4b07f02db6ae2d0","contributors":{"authors":[{"text":"Risser, Dennis W. 0000-0001-9597-5406 dwrisser@usgs.gov","orcid":"https://orcid.org/0000-0001-9597-5406","contributorId":898,"corporation":false,"usgs":true,"family":"Risser","given":"Dennis","email":"dwrisser@usgs.gov","middleInitial":"W.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282350,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gburek, William J.","contributorId":51381,"corporation":false,"usgs":true,"family":"Gburek","given":"William","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":282351,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Folmar, Gordon J.","contributorId":77601,"corporation":false,"usgs":true,"family":"Folmar","given":"Gordon","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":282352,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70392,"text":"ofr20051148 - 2005 - Acid-rock drainage at Skytop, Centre County, Pennsylvania, 2004","interactions":[],"lastModifiedDate":"2018-10-29T10:04:08","indexId":"ofr20051148","displayToPublicDate":"2005-04-15T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2005-1148","title":"Acid-rock drainage at Skytop, Centre County, Pennsylvania, 2004","docAbstract":"Recent construction for Interstate Highway 99 (I?99) exposed pyrite and associated Zn-Pb sulfide minerals beneath a >10-m thick gossan to oxidative weathering along a 40-60-m deep roadcut through a 270-m long section of the Ordovician Bald Eagle Formation at Skytop, near State College, Centre County, Pennsylvania. Nearby Zn-Pb deposits hosted in associated sandstone and limestone in Blair and Centre Counties were prospected in the past; however, these deposits generally were not viable as commercial mines. The pyritic sandstone from the roadcut was crushed and used locally as road base and fill for adjoining segments of I?99. Within months, acidic (pH<3), metal-laden seeps and runoff from the exposed cut and crushed sandstone raised concerns about surface- and ground-water contamination and prompted a halt in road construction and the beginning of costly remediation. Mineralized sandstones from the cut contain as much as 34 wt. % Fe, 28 wt. % S, 3.5 wt. % Zn, 1% wt. Pb, 88 ppm As, and 32 ppm Cd. A composite of <2 mm material sampled from the cut face contains 8.1 wt. % total sulfide S, 0.6 wt. % sulfate S, and is net acidic by acid-base accounting (net neutralization potential ?234 kg CaCO3/t). Primary sulfide minerals include pyrite, marcasite, sphalerite (2 to 12 wt. % Fe) and traces of chalcopyrite and galena. Pyrite occurs in mm- to cm-scale veinlets and disseminated grains in sandstone, as needles, and in a locally massive pyrite-cemented breccia along a fault. Inclusions (<10 ?m) of CdS and Ni-Co-As minerals in pyrite and minor amounts of Cd in sphalerite (0.1 wt. % or less) explain the primary source of trace metals in the rock and in associated secondary minerals and seepage. Wet/dry cycles associated with intermittent rainfall promoted oxidative weathering and dissolution of primary sulfides and their oxidation products. Resulting sulfate solutions evaporated during dry periods to form intermittent ?blooms? of soluble, yellow and white efflorescent sulfate salts (copiapite, melanterite, and halotrichite) on exposed rock and other surfaces. Salts coating the cut face incorporated Fe, Al, S, and minor Zn. They readily dissolved in deionized water in the laboratory to form solutions with pH <2.5, consistent with field observations. In addition to elevated dissolved Fe and sulfate concentrations (>1,000 mg/L), seep waters at the base of the cut contain >100 mg/L dissolved Zn and >1 mg/L As, Co, Cu, and Ni. Lead is relatively immobile (<10 ?g/L in seep waters). The salts sequester metals and acidity between rainfall events. Episodic salt dissolution then contributes pulses of contamination including acid to surface runoff and ground water. The Skytop experience highlights the need to understand dynamic interactions of mineralogy and hydrology in order to avoid potentially negative environmental impacts associated with excavation in sulfidic rocks.","language":"ENGLISH","doi":"10.3133/ofr20051148","usgsCitation":"Hammarstrom, J.M., Brady, K., and Cravotta, C.A., 2005, Acid-rock drainage at Skytop, Centre County, Pennsylvania, 2004 (Online Version 1.0): U.S. Geological Survey Open-File Report 2005-1148, 45 p., https://doi.org/10.3133/ofr20051148.","productDescription":"45 p.","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":192569,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6939,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2005/1148/","linkFileType":{"id":5,"text":"html"}}],"edition":"Online Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699d86","contributors":{"authors":[{"text":"Hammarstrom, Jane M. 0000-0003-2742-3460 jhammars@usgs.gov","orcid":"https://orcid.org/0000-0003-2742-3460","contributorId":1226,"corporation":false,"usgs":true,"family":"Hammarstrom","given":"Jane","email":"jhammars@usgs.gov","middleInitial":"M.","affiliations":[{"id":387,"text":"Mineral Resources Program","active":true,"usgs":true},{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":282333,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brady, Keith","contributorId":92764,"corporation":false,"usgs":true,"family":"Brady","given":"Keith","affiliations":[],"preferred":false,"id":282335,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cravotta, Charles A. III, 0000-0003-3116-4684 cravotta@usgs.gov","orcid":"https://orcid.org/0000-0003-3116-4684","contributorId":2193,"corporation":false,"usgs":true,"family":"Cravotta","given":"Charles","suffix":"III,","email":"cravotta@usgs.gov","middleInitial":"A.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":false,"id":282334,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70391,"text":"sir20055024 - 2005 - Evaluation of ground-water flow and land-surface subsidence caused by hypothetical withdrawals in the northern part of the Gulf Coast Aquifer system, Texas","interactions":[],"lastModifiedDate":"2017-05-24T17:40:14","indexId":"sir20055024","displayToPublicDate":"2005-04-15T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2005-5024","title":"Evaluation of ground-water flow and land-surface subsidence caused by hypothetical withdrawals in the northern part of the Gulf Coast Aquifer system, Texas","docAbstract":"During 2003–04 the U.S. Geological Survey, in cooperation with the Texas Water Development Board (TWDB) and the Harris-Galveston Coastal Subsidence District (HGCSD), used the previously developed Northern Gulf Coast Ground-Water Availability Modeling (NGC GAM) model to evaluate the effects of hypothetical projected withdrawals on ground-water flow in the northern part of the Gulf Coast aquifer system and land-surface subsidence in the NGC GAM model area of Texas. The Gulf Coast aquifer system comprises, from the surface, the Chicot and Evangeline aquifers, the Burkeville confining unit, the Jasper aquifer, and the Catahoula confining unit. Two withdrawal scenarios were simulated. The first scenario comprises historical withdrawals from the aquifer system for 1891–2000 and hypothetical projected withdrawals for 2001–50 compiled by the TWDB (TWDB scenario). The projected withdrawals compiled by the TWDB are based on ground-water demands estimated by regional water planning groups. The second scenario is a “merge” of the TWDB scenario with an alternate set of projected withdrawals from the Chicot and Evangeline aquifers in the Houston metropolitan area for 1995–2030 provided by the HGCSD (HGCSD scenario).
Under the TWDB scenario withdrawals from the entire system are projected to be about the same in 2050 as in 2000. The simulated potentiometric surfaces of the Chicot aquifer for 2010, 2020, 2030, 2040, and 2050 show relatively little change in configuration from the simulated 2000 potentiometric surface (maximum water-level depths in southern Harris County 150–200 feet below NGVD 29). The simulated decadal potentiometric surfaces of the Evangeline aquifer show the most change between 2000 and 2010. The area of water levels 250– 400 feet below NGVD 29 in western Harris County in 2000 shifts southeastward to southern Harris County, and water levels recover to 200–250 feet below NGVD 29 by 2010. Water levels in southern Harris County recover to 150–200 feet below NGVD 29 by 2020 and remain in that range through 2050. A relatively small cone of depression in southern Montgomery County that did not appear in the 2000 surface develops and enlarges during the projected period, with a maximum depth of 250–300 feet below NGVD 29 in 2030, 2040, and 2050. The simulated decadal potentiometric surfaces of the Jasper aquifer each have a major cone of depression centered in southern Montgomery County that was minimally developed in 2000 but reaches depths of 550–650 feet below NGVD 29 in the 2020, 2030, 2040, and 2050 surfaces. Under the TWDB scenario the percentage of withdrawals supplied by net recharge increases from 75 percent in 2000 to 87 percent in 2050, and the percentage of withdrawals supplied by storage decreases from 25 percent in 2000 to 13 percent in 2050.
Under the HGCSD scenario, withdrawals from the Chicot and Evangeline aquifers increase about 74 percent during 1995–2030; Jasper aquifer withdrawals are unchanged from those of the TWDB scenario. For the 2010, 2020, and 2030 potentiometric surfaces of the Chicot and Evangeline aquifers, the substantially greater withdrawals of the HGCSD scenario relative to those of the TWDB scenario result in progressively deeper cones of depression than those in the potentiometric surfaces associated with the TWDB scenario—for the Chicot aquifer in southern Harris County, 400–450 feet below NGVD 29 in 2030; for the Evangeline aquifer in southern Montgomery County, 700–750 feet below NGVD 29 in 2030. Although Jasper aquifer withdrawals are the same for both scenarios, the major cone of depression centered in southern Montgomery County in the 2030 potentiometric surface is 50 feet deeper at its center (600–700 feet below NGVD 29) than the cone in the 2030 surface under the TWDB scenario. Under the HGCSD scenario, the percentage of withdrawals supplied by net recharge decreases from 72 percent in 1995 to 57 percent in 2030, and the percentage of withdrawals supplied by storage increases from 28 percent in 2000 to 43 percent in 2030. About 85 percent of the increase supplied by storage is from the compaction of clay.
Land-surface subsidence in the major area of subsidence centered in Harris and Galveston Counties during 2000–50 that results from simulating the TWDB withdrawal scenario expands slightly to the west and increases in places. The maximum change occurs in the Conroe area where subsidence increases from about 4 to about 13 feet during the projected period. Land-surface subsidence in the major area of subsidence during 1995–2030 that results from simulating the HGCSD withdrawal scenario increases substantially. For example, in east-central Harris County maximum subsidence increases from about 10–11 feet in 1995 to 22 feet in 2030.
The hypothetical projected withdrawal scenarios are estimates of future withdrawals and might not represent actual future withdrawals. The simplifying assumptions that the downdip limit of freshwater flow in each hydrogeologic unit is a stable, sharp interface across which no flow occurs and that the base of the system is a no-flow boundary become less realistic and thus increase the uncertainty in results as drawdowns increase. The presence of uncertainty dictates that the results of the predictive simulations described in this report be used with caution in any decision-making process.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20055024","collaboration":"Prepared in cooperation with the Texas Water Development Board and the Harris-Galveston Coastal Subsidence District ","usgsCitation":"Kasmarek, M.C., Reece, B.D., and Houston, N.A., 2005, Evaluation of ground-water flow and land-surface subsidence caused by hypothetical withdrawals in the northern part of the Gulf Coast Aquifer system, Texas: U.S. Geological Survey Scientific Investigations Report 2005-5024, vi, 70 p., https://doi.org/10.3133/sir20055024.","productDescription":"vi, 70 p.","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":192568,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6938,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/sir2005-5024/","linkFileType":{"id":5,"text":"html"}},{"id":341752,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2005/5024/pdf/sir2005-5024.pdf","text":"Report","size":"13.0 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Texas","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -94.141845703125,\n 31.89621446335144\n ],\n [\n -97.734375,\n 29.76437737516313\n ],\n [\n -96.26220703125,\n 28.110748760633534\n ],\n [\n -92.867431640625,\n 30.107117887092357\n ],\n [\n -94.141845703125,\n 31.89621446335144\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fbe4b07f02db5f4990","contributors":{"authors":[{"text":"Kasmarek, Mark C. 0000-0003-2808-2506 mckasmar@usgs.gov","orcid":"https://orcid.org/0000-0003-2808-2506","contributorId":1968,"corporation":false,"usgs":true,"family":"Kasmarek","given":"Mark","email":"mckasmar@usgs.gov","middleInitial":"C.","affiliations":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282331,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reece, Brian D. bdreece@usgs.gov","contributorId":2129,"corporation":false,"usgs":true,"family":"Reece","given":"Brian","email":"bdreece@usgs.gov","middleInitial":"D.","affiliations":[],"preferred":true,"id":282332,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Houston, Natalie A. 0000-0002-6071-4545 nhouston@usgs.gov","orcid":"https://orcid.org/0000-0002-6071-4545","contributorId":1682,"corporation":false,"usgs":true,"family":"Houston","given":"Natalie","email":"nhouston@usgs.gov","middleInitial":"A.","affiliations":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282330,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70395,"text":"sir20055042 - 2005 - Effects of historical coal mining and drainage from abandoned mines on streamflow and water quality in Bear Creek, Dauphin County, Pennsylvania — March 1999–December 2002","interactions":[],"lastModifiedDate":"2022-01-11T20:41:46.353971","indexId":"sir20055042","displayToPublicDate":"2005-04-15T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2005-5042","title":"Effects of historical coal mining and drainage from abandoned mines on streamflow and water quality in Bear Creek, Dauphin County, Pennsylvania — March 1999–December 2002","docAbstract":"More than 100 years of anthracite coal mining has changed surface- and ground-water hydrology and contaminated streams draining the Southern Anthracite Coal Field in east-central Pennsylvania. Bear Creek drains the western prong of the Southern Anthracite Coal Field and is affected by metals in drainage from abandoned mines and streamwater losses. Total Maximum Daily Loads (TMDL) developed for dissolved iron of about 5 lb/d (pounds per day) commonly are exceeded in the reach downstream of mine discharges. Restoration of Bear Creek using aerobic ponds to passively remove iron in abandoned mine drainage is under consideration (2004) by the Dauphin County Conservation District. This report, prepared in cooperation with the Dauphin County Conservation District, evaluates chemical and hydrologic data collected in Bear Creek and its receiving waters prior to implementation of mine-drainage treatment. The data collected represent the type of baseline information needed for documentation of water-quality changes following passive treatment of mine drainage in Pennsylvania and in other similar hydrogeologic settings.\r\n\r\nSeven surface-water sites on Bear Creek and two mine discharges were monitored for nearly three years to characterize the chemistry and hydrology of the following: (1) Bear Creek upstream of the mine discharges (BC-UMD), (2) water draining from the Lykens-Williamstown Mine Pool at the Lykens Water-Level Tunnel (LWLT) and Lykens Drift (LD) discharges, (3) Bear Creek after mixing with the mine discharges (BC-DMD), and (4) Bear Creek prior to mixing with Wiconisco Creek (BCM). Two sites on Wiconisco Creek, upstream and downstream of Bear Creek (WC-UBC and WC-DBC, respectively), were selected to evaluate changes in streamflow and water quality upon mixing with Bear Creek. \r\n\r\nDuring periods of below-normal precipitation, streamwater loss was commonly 100 percent upstream of site BC-UMD (streamflow range = 0 to 9.7 ft3/s (cubic feet per second)) but no loss was detected downstream owing to sustained mine water drainage from the Lykens Water-Level Tunnel (range = 0.41 to 3.7 ft3/s), Lykens Drift (range = 0.40 to 6.1 ft3/s), and diffuse zones of seepage. Collectively, mine water inputs contributed about 84 percent of base flow and 53 percent of stormflow measured in the downstream reach. \r\nAn option under consideration by the Dauphin County Conservation District for treatment of the discharge from the LWLT requires the source of the discharge to be captured and rerouted downstream, bypassing approximately 1,000 feet of stream channel. Because streamwater loss upstream of the tunnel was commonly 100 percent, rerouting the discharge from the LWLT may extend the reach of Bear Creek that is subject to dryness. \r\n\r\nDifferences in the chemistry of water discharging from the LWLT compared to the LD suggest that the flow path through the Lykens-Williamstown Mine Pool to each mine discharge is unique. The LWLT is marginally alkaline (median net acid neutralizing capacity (ANC) = 9 mg/L (milligrams per liter) as CaCO3; median pH = 5.9), commonly becomes acidic (minimum net ANC = -74 mg/L as CaCO3) at low flow, and may benefit from alkaline amendments prior to passive treatment. Water discharging from the LD provides excess ANC (median net ANC = 123 mg/L as CaCO3; median pH = 6.5) to the downstream reach and is nearly anoxic at its source (median dissolved oxygen = 0.5 mg/L). Low dissolved oxygen water with relatively high ANC and metals concentrations discharging from the LD is characteristic of a deeper flow path and longer residence time within the mine pool than the more acidic, oxygenated water discharging from the LWLT.\r\n\r\nTMDLs for iron have been developed for dissolved species only. Consequently, distinguishing between dissolved and suspended iron in Bear Creek is important for evaluating water-quality improvement through TMDL attainment. Median total iron concentration increased from 550 mg/L (micrograms per liter) at site BC-UM","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20055042","usgsCitation":"Chaplin, J.J., 2005, Effects of historical coal mining and drainage from abandoned mines on streamflow and water quality in Bear Creek, Dauphin County, Pennsylvania — March 1999–December 2002: U.S. Geological Survey Scientific Investigations Report 2005-5042, 51 p., https://doi.org/10.3133/sir20055042.","productDescription":"51 p.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":6942,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/sir2005-5042/","linkFileType":{"id":5,"text":"html"}},{"id":192612,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":394211,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_71628.htm"}],"country":"United States","state":"Pennsylvania","county":"Dauphin County","otherGeospatial":"Bear Creek","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.7061,\n 40.5667\n ],\n [\n -76.6894,\n 40.5667\n ],\n [\n -76.6894,\n 40.5892\n ],\n [\n -76.7061,\n 40.5892\n ],\n [\n -76.7061,\n 40.5667\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a29e4b07f02db611ecd","contributors":{"authors":[{"text":"Chaplin, Jeffrey J. 0000-0002-0617-5050 jchaplin@usgs.gov","orcid":"https://orcid.org/0000-0002-0617-5050","contributorId":147,"corporation":false,"usgs":true,"family":"Chaplin","given":"Jeffrey","email":"jchaplin@usgs.gov","middleInitial":"J.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282340,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70364,"text":"ofr20051062 - 2005 - Reconnaissance gas measurements on the East Rift Zone of Kilauea Volcano, Hawai'i by Fourier transform infrared spectroscopy","interactions":[],"lastModifiedDate":"2019-05-07T09:53:01","indexId":"ofr20051062","displayToPublicDate":"2005-04-06T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2005-1062","title":"Reconnaissance gas measurements on the East Rift Zone of Kilauea Volcano, Hawai'i by Fourier transform infrared spectroscopy","docAbstract":"We report the results of a set of measurements of volcanic gases on two small ground level plumes in the vicinity of Pu`u `O`o cone on the middle East Rift Zone (ERZ) of Kilauea volcano, Hawai`i on 15 June 2001 using open-path Fourier transform infrared (FTIR) spectroscopy. The work was carried out as a reconnaissance survey to assess the monitoring and research value of FTIR measurements at this volcano. Despite representing emissions of residual volatiles from lava that has undergone prior degassing, the plumes contained detectable amounts of CO2, CO, SO2, HCl, HF and SiF4. Various processes, including subsurface cooling, condensation of water in the atmospheric plume, oxidation, dissolution in water, and reactions with wall rocks at plume vents affect the abundance of these gases. Low concentrations of volcanic CO2 measured against a high ambient background are not well constrained by FTIR spectroscopy. Although there appear to be some differences between these gases and Pu`u `O`o source gases, ratios of HCl/SO2, HF/SO2 and CO/SO2 determined by FTIR measurements of these two small plumes compare reasonably well with earlier published analyses of ERZ vent samples. The measurements yielded emission rate estimates of 4, 11 and 4 t d-1","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20051062","usgsCitation":"McGee, K.A., Elias, T., Sutton, A.J., Doukas, M.P., Zemek, P.G., and Gerlach, T.M., 2005, Reconnaissance gas measurements on the East Rift Zone of Kilauea Volcano, Hawai'i by Fourier transform infrared spectroscopy (Version 1.0): U.S. Geological Survey Open-File Report 2005-1062, 28 p., https://doi.org/10.3133/ofr20051062.","productDescription":"28 p.","costCenters":[{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true}],"links":[{"id":186326,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6526,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2005/1062/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Hawaii","otherGeospatial":"Kılauea volcano","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -155.3144073486328,\n 19.276146935787732\n ],\n [\n -155.1605987548828,\n 19.276146935787732\n ],\n [\n -155.1605987548828,\n 19.47241867420536\n ],\n [\n -155.3144073486328,\n 19.47241867420536\n ],\n [\n -155.3144073486328,\n 19.276146935787732\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a73e4b07f02db643f0e","contributors":{"authors":[{"text":"McGee, Kenneth A. kenmcgee@usgs.gov","contributorId":2135,"corporation":false,"usgs":true,"family":"McGee","given":"Kenneth","email":"kenmcgee@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":282290,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Elias, Tamar 0000-0002-9592-4518 telias@usgs.gov","orcid":"https://orcid.org/0000-0002-9592-4518","contributorId":3916,"corporation":false,"usgs":true,"family":"Elias","given":"Tamar","email":"telias@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":282292,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sutton, A. Jefferson","contributorId":47860,"corporation":false,"usgs":true,"family":"Sutton","given":"A.","email":"","middleInitial":"Jefferson","affiliations":[],"preferred":false,"id":282295,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Doukas, Michael P. mdoukas@usgs.gov","contributorId":2686,"corporation":false,"usgs":true,"family":"Doukas","given":"Michael","email":"mdoukas@usgs.gov","middleInitial":"P.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":282291,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Zemek, Peter G.","contributorId":32244,"corporation":false,"usgs":true,"family":"Zemek","given":"Peter","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":282294,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Gerlach, Terrence M.","contributorId":30246,"corporation":false,"usgs":true,"family":"Gerlach","given":"Terrence","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":282293,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":70363,"text":"pp1701 - 2005 - Tephra layers of Blind Spring Valley and related upper Pliocene and Pleistocene tephra layers, California, Nevada, and Utah: Isotopic ages, correlation, and magnetostratigraphy","interactions":[],"lastModifiedDate":"2024-10-30T20:45:02.248751","indexId":"pp1701","displayToPublicDate":"2005-04-06T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1701","title":"Tephra layers of Blind Spring Valley and related upper Pliocene and Pleistocene tephra layers, California, Nevada, and Utah: Isotopic ages, correlation, and magnetostratigraphy","docAbstract":"Numerical ages have been determined for a stratigraphic sequence of silicic tephra layers exposed at the Cowan Pumice Mine in Blind Spring Valley, near Benton Hot Springs, east-central California, as well as at Chalk Cliffs, north of Bishop, Calif. The tephra layers at these sites were deposited after eruptions from nearby sources, most of them from near Glass Mountain, and some from unknown sources. The ages were determined primarily by the laser-fusion 40Ar/39Ar method, mostly on sanidine feldspar; two were determined by conventional K-Ar analysis on obsidian clasts.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1701","usgsCitation":"Sarna-Wojcicki, A.M., Reheis, M., Pringle, M.S., Fleck, R.J., Burbank, D., Meyer, C.E., Slate, J.L., Wan, E., Budahn, J.R., Troxel, B., and Walker, J.P., 2005, Tephra layers of Blind Spring Valley and related upper Pliocene and Pleistocene tephra layers, California, Nevada, and Utah: Isotopic ages, correlation, and magnetostratigraphy: U.S. Geological Survey Professional Paper 1701, v, 63 p., https://doi.org/10.3133/pp1701.","productDescription":"v, 63 p.","numberOfPages":"69","costCenters":[{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true}],"links":[{"id":186325,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6525,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/pp1701/","linkFileType":{"id":5,"text":"html"}},{"id":463448,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_70954.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"California, Nevada, Utah","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124.71679687499999,\n 34.016241889667015\n ],\n [\n -113.3349609375,\n 34.016241889667015\n ],\n [\n -113.3349609375,\n 39.232253141714885\n ],\n [\n -124.71679687499999,\n 39.232253141714885\n ],\n [\n -124.71679687499999,\n 34.016241889667015\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db685128","contributors":{"authors":[{"text":"Sarna-Wojcicki, Andrei M. 0000-0002-0244-9149 asarna@usgs.gov","orcid":"https://orcid.org/0000-0002-0244-9149","contributorId":1046,"corporation":false,"usgs":true,"family":"Sarna-Wojcicki","given":"Andrei","email":"asarna@usgs.gov","middleInitial":"M.","affiliations":[],"preferred":true,"id":282280,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reheis, Marith C. 0000-0002-8359-323X","orcid":"https://orcid.org/0000-0002-8359-323X","contributorId":101244,"corporation":false,"usgs":true,"family":"Reheis","given":"Marith C.","affiliations":[],"preferred":false,"id":282289,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pringle, Malcolm S.","contributorId":12929,"corporation":false,"usgs":true,"family":"Pringle","given":"Malcolm","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":282284,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Fleck, Robert J. 0000-0002-3149-8249 fleck@usgs.gov","orcid":"https://orcid.org/0000-0002-3149-8249","contributorId":1048,"corporation":false,"usgs":true,"family":"Fleck","given":"Robert","email":"fleck@usgs.gov","middleInitial":"J.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":282281,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Burbank, Doug","contributorId":56732,"corporation":false,"usgs":true,"family":"Burbank","given":"Doug","email":"","affiliations":[],"preferred":false,"id":282287,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Meyer, Charles E.","contributorId":84007,"corporation":false,"usgs":true,"family":"Meyer","given":"Charles","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":282288,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Slate, Janet L. 0000-0002-2870-9068 jslate@usgs.gov","orcid":"https://orcid.org/0000-0002-2870-9068","contributorId":252,"corporation":false,"usgs":true,"family":"Slate","given":"Janet","email":"jslate@usgs.gov","middleInitial":"L.","affiliations":[{"id":501,"text":"Office of Science Quality and Integrity","active":true,"usgs":true}],"preferred":true,"id":282279,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Wan, Elmira 0000-0002-9255-112X ewan@usgs.gov","orcid":"https://orcid.org/0000-0002-9255-112X","contributorId":3434,"corporation":false,"usgs":true,"family":"Wan","given":"Elmira","email":"ewan@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":282283,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Budahn, James R. 0000-0001-9794-8882 jbudahn@usgs.gov","orcid":"https://orcid.org/0000-0001-9794-8882","contributorId":1175,"corporation":false,"usgs":true,"family":"Budahn","given":"James","email":"jbudahn@usgs.gov","middleInitial":"R.","affiliations":[{"id":171,"text":"Central Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":282282,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Troxel, Bennie","contributorId":41904,"corporation":false,"usgs":true,"family":"Troxel","given":"Bennie","affiliations":[],"preferred":false,"id":282285,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Walker, James P.","contributorId":55083,"corporation":false,"usgs":true,"family":"Walker","given":"James","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":282286,"contributorType":{"id":1,"text":"Authors"},"rank":11}]}} ,{"id":70003889,"text":"70003889 - 2005 - 87Sr/86Sr sourcing of ponderosa pine used in Anasazi great house construction at Chaco Canyon, New Mexico","interactions":[],"lastModifiedDate":"2020-08-31T16:33:06.135745","indexId":"70003889","displayToPublicDate":"2005-04-05T12:59:01","publicationYear":"2005","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2182,"text":"Journal of Archaeological Science","active":true,"publicationSubtype":{"id":10}},"displayTitle":"87Sr/86Sr sourcing of ponderosa pine used in Anasazi great house construction at Chaco Canyon, New Mexico","title":"87Sr/86Sr sourcing of ponderosa pine used in Anasazi great house construction at Chaco Canyon, New Mexico","docAbstract":"Previous analysis of 87Sr/86Sr ratios shows that 10th through 12th century Chaco Canyon was provisioned with plant materials that came from more than 75 km away. This includes (1) corn (Zea mays) grown on the eastern flanks of the Chuska Mountains and floodplain of the San Juan River to the west and north, and (2) spruce (Picea sp.) and fir (Abies sp.) beams from the crest of the Chuska and San Mateo Mountains to the west and south. Here, we extend 87Sr/86Sr analysis to ponderosa pine (Pinus ponderosa) prevalent in the architectural timber at three of the Chacoan great houses (Pueblo Bonito, Chetro Ketl, Pueblo del Arroyo). Like the architectural spruce and fir, much of the ponderosa matches the 87Sr/86Sr ratios of living trees in the Chuska Mountains. Many of the architectural ponderosa, however, have similar ratios to living trees in the La Plata and San Juan Mountains to the north and Lobo Mesa/Hosta Butte to the south. There are no systematic patterns in spruce/fir or ponderosa provenance by great house or time, suggesting the use of stockpiles from a few preferred sources. The multiple and distant sources for food and timber, now based on hundreds of isotopic values from modern and archeological samples, confirm conventional wisdom about the geographic scope of the larger Chacoan system. The complexity of this procurement warns against simple generalizations based on just one species, a single class of botanical artifact, or a few isotopic values.","language":"English","publisher":"Elsevier","publisherLocation":"London","doi":"10.1016/j.jas.2005.01.016","usgsCitation":"Reynolds, A.C., Betancourt, J.L., Quade, J., Patchett, P.J., Dean, J.S., and Stein, J., 2005, 87Sr/86Sr sourcing of ponderosa pine used in Anasazi great house construction at Chaco Canyon, New Mexico: Journal of Archaeological Science, v. 32, no. 7, p. 1061-1075, https://doi.org/10.1016/j.jas.2005.01.016.","productDescription":"15 p.","startPage":"1061","endPage":"1075","costCenters":[{"id":148,"text":"Branch of Regional Research-Western Region","active":false,"usgs":true}],"links":[{"id":203839,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Mexico","otherGeospatial":"Chaco Canyon","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.01054000854491,\n 36.00786740304298\n ],\n [\n -107.85346984863281,\n 36.00786740304298\n ],\n [\n -107.85346984863281,\n 36.08448256814837\n ],\n [\n -108.01054000854491,\n 36.08448256814837\n ],\n [\n -108.01054000854491,\n 36.00786740304298\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"32","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b42e9","contributors":{"authors":[{"text":"Reynolds, Amanda C.","contributorId":71680,"corporation":false,"usgs":true,"family":"Reynolds","given":"Amanda","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":349317,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Betancourt, Julio L. 0000-0002-7165-0743 jlbetanc@usgs.gov","orcid":"https://orcid.org/0000-0002-7165-0743","contributorId":3376,"corporation":false,"usgs":true,"family":"Betancourt","given":"Julio","email":"jlbetanc@usgs.gov","middleInitial":"L.","affiliations":[{"id":554,"text":"Science and Decisions Center","active":true,"usgs":true},{"id":438,"text":"National Research Program - Western Branch","active":true,"usgs":true},{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"preferred":true,"id":349315,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Quade, Jay","contributorId":104197,"corporation":false,"usgs":true,"family":"Quade","given":"Jay","email":"","affiliations":[],"preferred":false,"id":349320,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Patchett, P. Jonathan","contributorId":80225,"corporation":false,"usgs":true,"family":"Patchett","given":"P.","email":"","middleInitial":"Jonathan","affiliations":[],"preferred":false,"id":349318,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Dean, Jeffery S.","contributorId":93612,"corporation":false,"usgs":true,"family":"Dean","given":"Jeffery","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":349319,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Stein, John","contributorId":70527,"corporation":false,"usgs":true,"family":"Stein","given":"John","email":"","affiliations":[],"preferred":false,"id":349316,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":70351,"text":"ofr20051125 - 2005 - Radiochemical and chemical constituents in water from selected wells and springs from the southern boundary of the Idaho National Laboratory to the Hagerman Area, Idaho, 2003","interactions":[],"lastModifiedDate":"2012-02-02T00:13:48","indexId":"ofr20051125","displayToPublicDate":"2005-04-05T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2005-1125","title":"Radiochemical and chemical constituents in water from selected wells and springs from the southern boundary of the Idaho National Laboratory to the Hagerman Area, Idaho, 2003","docAbstract":"The U.S. Geological Survey and the Idaho Department of Water Resources, in cooperation with the U.S. Department of Energy, sampled water from 14 sites as part of an ongoing study to monitor the water quality of the eastern Snake River Plain aquifer between the southern boundary of the Idaho National Laboratory (INL) and the Burley-Twin Falls-Hagerman area. The State of Idaho, Department of Environmental Quality, Division of INL Oversight and Radiation Control cosampled with the U.S. Geological Survey and the Idaho Department of Water Resources and their analytical results are included in this report. The samples were collected from four domestic wells, two dairy wells, two springs, four irrigation wells, one observation well, and one stock well and analyzed for selected radiochemical and chemical constituents. Two quality-assurance samples, sequential replicates, also were collected and analyzed. \r\n\r\nNone of the concentrations of radiochemical or organic-chemical constituents exceeded the maximum contaminant levels for drinking water established by the U.S. Environmental Protection Agency. However, the concentration of one inorganic-chemical constituent, nitrate (as nitrogen), in water from site MV-43 was 20 milligrams per liter which exceeded the maximum contaminant level for that constituent. Of the radiochemical and chemical concentrations analyzed for in the replicate-sample pairs, 267 of the 270 pairs (with 95 percent confidence) were statistically equivalent.","language":"ENGLISH","doi":"10.3133/ofr20051125","usgsCitation":"Rattray, G.W., Wehnke, A.J., Hall, L.F., and Campbell, L.J., 2005, Radiochemical and chemical constituents in water from selected wells and springs from the southern boundary of the Idaho National Laboratory to the Hagerman Area, Idaho, 2003: U.S. Geological Survey Open-File Report 2005-1125, 30 p., https://doi.org/10.3133/ofr20051125.","productDescription":"30 p.","costCenters":[],"links":[{"id":185769,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6500,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2005/1125/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5fe4b07f02db634953","contributors":{"authors":[{"text":"Rattray, Gordon W. 0000-0002-1690-3218 grattray@usgs.gov","orcid":"https://orcid.org/0000-0002-1690-3218","contributorId":2521,"corporation":false,"usgs":true,"family":"Rattray","given":"Gordon","email":"grattray@usgs.gov","middleInitial":"W.","affiliations":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282249,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wehnke, Amy J. 0000-0003-1237-052X ajwehnke@usgs.gov","orcid":"https://orcid.org/0000-0003-1237-052X","contributorId":5660,"corporation":false,"usgs":true,"family":"Wehnke","given":"Amy","email":"ajwehnke@usgs.gov","middleInitial":"J.","affiliations":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282250,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hall, L. Flint","contributorId":53464,"corporation":false,"usgs":true,"family":"Hall","given":"L.","email":"","middleInitial":"Flint","affiliations":[],"preferred":false,"id":282251,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Campbell, Linford J.","contributorId":77174,"corporation":false,"usgs":true,"family":"Campbell","given":"Linford","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":282252,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70266,"text":"cir1280 - 2005 - Water resources and the urban environment, lower Charles River watershed, Massachusetts, 1630-2005","interactions":[],"lastModifiedDate":"2022-02-11T16:58:00.423862","indexId":"cir1280","displayToPublicDate":"2005-03-21T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1280","title":"Water resources and the urban environment, lower Charles River watershed, Massachusetts, 1630-2005","docAbstract":"The Charles River, one of the Nation’s most historically significant rivers, flows through the center of the Boston metropolitan region in eastern Massachusetts. The lower Charles River, downstream of the original head of tide in Watertown, was originally a productive estuary and important source of fish and shellfish for the Native Americans of the region. This portion of the river has an exceptionally long and colorful human history. In 1615, the explorer Captain John Smith gave the river its modern name, in honor of young Prince Charles of England. In 1617–18, the Native American community of the watershed was decimated by an epidemic, after having continuously occupied the area for the previous 4,000 years. In 1630, the first large group of English settlers, led by John Winthrop, set foot on the Shawmut Peninsula at the mouth of the river, and established the town of Boston. In the 1630s, the first printing press, public park, public school, and college in the English colonies were all established on the banks of the Charles River. Almost immediately, the settlers of Boston and adjacent towns also began to modify the landscape and water resources of the watershed.
Perhaps the most important type of landscape alteration in the watershed was the filling of the extensive salt marshes and tidal flats of the estuary downstream of Watertown. This landmaking activity along the lower Charles River began in the mid-1600s, and did not conclude until the 1950s. In the early 20th century, the estuary mouth was dammed, creating a freshwater basin in the lower 9.5 miles of the river. A system of parks and parkways was built along the banks of the impounded river. In addition to the mainstem river, virtually all of the remaining water resources in the watershed have also been altered. Most of the river’s tributaries, for example, were culverted, or placed into tunnels, and many of the ponds and freshwater wetlands in the watershed were filled to facilitate urban development.
One additional legacy of the river’s long human history is pollution from industry and sewage. By 1875, a total of 43 mills were operating along the lower Charles River between Watertown Dam and Boston Harbor. Thousands of gallons of untreated sewage and industrial wastewater entered the river daily through gravity drains, posing a major threat to public health. Concerted efforts to address the sewage problem began in the late 1870s. By the 1960s, the water quality of the river was significantly improved, yet still not suitable for swimming, fishing, or even boating under most conditions. In 1965, the Charles River Watershed Association was organized and the call to restore the environmental quality of the river and its parklands was heard anew. Passage of the Federal Clean Water Act in 1972 and the subsequent court-ordered reconstruction of the region’s sewage-treatment infrastructure in the 1980s and 1990s (the “Boston Harbor Cleanup”) provided additional impetus to address the river’s remaining pollution problems.
In 1995, the U.S. Environmental Protection Agency launched the Clean Charles 2005 Initiative, which brought together government agencies, private-sector institutions, and environmental organizations to focus on restoring the river to fishable and swimmable conditions by Earth Day 2005. This initiative has achieved substantial improvements in water quality; sewage discharges to the river, for example, have been largely eliminated. Nevertheless, it is now widely acknowledged that full attainment of water-quality standards will likely depend upon improved public understanding of the watershed, continued efforts to eliminate illicit sewage discharges to the river, and better management of the urban runoff that enters the river both directly and from its many tributary streams.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir1280","isbn":"0607968540","collaboration":"Prepared in cooperation with the U.S. Environmental Protection Agency and the Massachusetts Department of Environmental Protection","usgsCitation":"Weiskel, P.K., Barlow, L.K., and Smieszek, T.W., 2005, Water resources and the urban environment, lower Charles River watershed, Massachusetts, 1630-2005: U.S. Geological Survey Circular 1280, v, 46 p., https://doi.org/10.3133/cir1280.","productDescription":"v, 46 p.","costCenters":[],"links":[{"id":6959,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/circ/2005/1280/","linkFileType":{"id":5,"text":"html"}},{"id":186008,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/2005/1280/images/cover_sm.gif"},{"id":395460,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/2005/1280/pdf/cir1280.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Massachusetts","otherGeospatial":"Lower Charles River watershed","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -71.21578216552733,\n 42.22139878761366\n ],\n [\n -71.0321044921875,\n 42.22139878761366\n ],\n [\n -71.0321044921875,\n 42.404953126475725\n ],\n [\n -71.21578216552733,\n 42.404953126475725\n ],\n [\n -71.21578216552733,\n 42.22139878761366\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a05e4b07f02db5f8657","contributors":{"authors":[{"text":"Weiskel, Peter K. pweiskel@usgs.gov","contributorId":1099,"corporation":false,"usgs":true,"family":"Weiskel","given":"Peter","email":"pweiskel@usgs.gov","middleInitial":"K.","affiliations":[{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true},{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282074,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Barlow, Lora K.","contributorId":90279,"corporation":false,"usgs":true,"family":"Barlow","given":"Lora","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":282076,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Smieszek, Tomas W. 0000-0002-1361-2167","orcid":"https://orcid.org/0000-0002-1361-2167","contributorId":241661,"corporation":false,"usgs":true,"family":"Smieszek","given":"Tomas","email":"","middleInitial":"W.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282075,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70253,"text":"sir20045197 - 2005 - Simulation of ground-water flow in the basin-fill aquifer of the Tularosa Basin, south-central New Mexico, predevelopment through 2040","interactions":[],"lastModifiedDate":"2012-02-02T00:13:52","indexId":"sir20045197","displayToPublicDate":"2005-03-20T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2004-5197","title":"Simulation of ground-water flow in the basin-fill aquifer of the Tularosa Basin, south-central New Mexico, predevelopment through 2040","docAbstract":"The hydrology of the basin-fill aquifer in the Tularosa Basin was evaluated through construction and calibration of steady-state and transient three-dimensional ground-water-flow simulations. Simulations were made using the U.S. Geological Survey finite-difference modular ground-water-flow computer software MODFLOW-96. The transient simulation covered 1948-2040. Both steady-state and transient simulations were calibrated by matching simulation output to available ground-water-level measurements. The root-mean-square error of the steady-state calibration in the well-calibrated area of the ground-water-flow simulation was 6.3 meters, and root-mean-square errors of individual transient-calibration points ranged from 0.8 to 17.0 meters. The areal distribution of water-level measurements used in the steady-state and transient calibrations restricts the well-calibrated area of the model to the eastern side of the Tularosa Basin. Water levels in the La Luz Creek subbasin area were underestimated by both the steady-state and transient models, suggesting that the hydrology of this area is not well represented in the model.\r\n\r\nAbout 143,000 cubic meters per day of recharge is estimated to enter the basin-fill aquifer from subbasins that rim the Tularosa Basin. The estimated recharge is about 4-5 percent of total precipitation in most subbasins. Approximately 88 percent of total recharge left the basin-fill aquifer as evapotranspiration under predevelopment conditions.\r\n\r\nWater levels were simulated for 1948, 1995, and 2040 under scenarios of zero and maximum return flows. Estimated return flows from municipalities were calculated on the basis of data in the Tularosa Basin Regional Water Plan for 2000-2040. Agricultural return flows were estimated primarily on the basis of ground-water-withdrawal, ground-water-depletion, surface-water-withdrawal, and surface-water-depletion data for the Tularosa Basin. The ground-water-flow simulation was sensitive to the return-flow scenario in the agricultural area near Tularosa and decreasingly sensitive to the south. Declines in simulated water levels near Tularosa between 1948 and 1995 were as large as 30 meters under the zero return-flow scenario and 15 meters under the maximum return-flow scenario. Declines in simulated water levels between 1995 and 2040 were as large as 25 meters under the zero return-flow scenario and 15 meters under the maximum return-flow scenario. Comparison of water levels measured near Tularosa in 1991 and water levels simulated under the maximum return-flow scenario for 1991 suggests that declines in simulated water levels near Tularosa may be overestimated under the zero return-flow scenario. Declines in simulated water levels near the City of Alamogordo well field between 1948 and 1995 were as large as 15 meters under the zero return-flow scenario and 10 meters under the maximum return-flow scenario. Simulated declines in water levels between 1995 and 2040 were nearly 15 meters under both return-flow scenarios assuming that all projected increases in withdrawal came from existing City of Alamogordo public-supply wells and all withdrawal from the wells came from the basin-fill aquifer. Declines in simulated water levels near the Holloman Air Force Base well fields between 1948 and 1995 and between 1995 and 2040 were less than 5 meters under both the zero and maximum return-flow scenarios. In 1995 under the zero return-flow scenario, an estimated 56,000 cubic meters of water per day was removed from aquifer storage. Of the approximately 199,000 cubic meters of water per day that left the aquifer under 1995 conditions, 40 percent left the basin-fill aquifer as ground-water withdrawal, 51 percent as evapotranspiration, 7 percent by interbasin ground-water flow into the Hueco Bolson, and 2 percent by flow into creeks and springs.\r\n\r\nGeneralized directions of ground-water flow were simulated for 1948, 1995, and 2040 for much of the eastern part of the Tularosa Basin. 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","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Coastal Classification Atlas","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20051003","usgsCitation":"Morton, R., and Peterson, R.L., 2005, Coastal classification atlas: Southeastern Louisiana coastal classification maps -- Pass Abel to East Timbalier Island: U.S. Geological Survey Open-File Report 2005-1003, HTML Document; 1 CD-ROM, https://doi.org/10.3133/ofr20051003.","productDescription":"HTML Document; 1 CD-ROM","onlineOnly":"Y","costCenters":[{"id":186,"text":"Coastal and Marine Geology Program","active":true,"usgs":true}],"links":[{"id":188790,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":390618,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_70957.htm"},{"id":6248,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2005/1003/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Louisiana","otherGeospatial":"East Timbalier Island, Pass Abel","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.29525756835938,\n 29.084976575985912\n ],\n [\n -89.912109375,\n 29.084976575985912\n ],\n [\n -89.912109375,\n 29.27442054681336\n ],\n [\n -90.29525756835938,\n 29.27442054681336\n ],\n [\n -90.29525756835938,\n 29.084976575985912\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e73da","contributors":{"authors":[{"text":"Morton, Robert A.","contributorId":88333,"corporation":false,"usgs":true,"family":"Morton","given":"Robert A.","affiliations":[],"preferred":false,"id":281676,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Peterson, Russell L.","contributorId":55045,"corporation":false,"usgs":true,"family":"Peterson","given":"Russell","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":281675,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70217328,"text":"70217328 - 2005 - Structure and mechanics of the San Andreas–San Gregorio fault junction, San Francisco, California","interactions":[],"lastModifiedDate":"2021-01-15T21:02:57.911383","indexId":"70217328","displayToPublicDate":"2005-01-29T14:55:24","publicationYear":"2005","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":7143,"text":"Geochemistry, Geophysics, and Geosystems","active":true,"publicationSubtype":{"id":10}},"title":"Structure and mechanics of the San Andreas–San Gregorio fault junction, San Francisco, California","docAbstract":"[1] The right‐lateral San Gregorio and San Andreas faults meet west of the Golden Gate near San Francisco. Coincident seismic reflection and refraction profiling across the San Gregorio and San Andreas faults south of their junction shows the crust between them to have formed shallow extensional basins that are dissected by parallel strike‐slip faults. We employ a regional finite element model to investigate the long‐term consequences of the fault geometry. Over the course of 2–3 m.y. of slip on the San Andreas‐San Gregorio fault system, elongated extensional basins are predicted to form between the two faults. An additional consequence of the fault geometry is that the San Andreas fault is expected to have migrated eastward relative to the San Gregorio fault. We thus propose a model of eastward stepping right‐lateral fault formation to explain the observed multiple fault strands and depositional basins. The current manifestation of this process might be the observed transfer of slip from the San Andreas fault east to the Golden Gate fault.
","language":"English","publisher":"Wiley","doi":"10.1029/2004GC000838","usgsCitation":"Parsons, T., Bruns, T.R., and Sliter, R.W., 2005, Structure and mechanics of the San Andreas–San Gregorio fault junction, San Francisco, California: Geochemistry, Geophysics, and Geosystems, v. 6, no. 1, Q01009, 7 p., https://doi.org/10.1029/2004GC000838.","productDescription":"Q01009, 7 p.","costCenters":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":477682,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1029/2004gc000838","text":"Publisher Index Page"},{"id":382236,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"San Francisco","otherGeospatial":"San Andreas-San Gregorio fault junction","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.5638198852539,\n 37.77017196507861\n ],\n [\n -122.48004913330077,\n 37.77017196507861\n ],\n [\n -122.48004913330077,\n 37.8271414168374\n ],\n [\n -122.5638198852539,\n 37.8271414168374\n ],\n [\n -122.5638198852539,\n 37.77017196507861\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"6","issue":"1","noUsgsAuthors":false,"publicationDate":"2005-01-29","publicationStatus":"PW","contributors":{"authors":[{"text":"Parsons, Tom 0000-0002-0582-4338","orcid":"https://orcid.org/0000-0002-0582-4338","contributorId":22056,"corporation":false,"usgs":true,"family":"Parsons","given":"Tom","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":808366,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bruns, Terry R.","contributorId":29420,"corporation":false,"usgs":true,"family":"Bruns","given":"Terry","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":808367,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sliter, Ray W. 0000-0003-0337-3454 rsliter@usgs.gov","orcid":"https://orcid.org/0000-0003-0337-3454","contributorId":1992,"corporation":false,"usgs":true,"family":"Sliter","given":"Ray","email":"rsliter@usgs.gov","middleInitial":"W.","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":808368,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70242740,"text":"pp1688I - 2005 - High-resolution seismic-reflection image of the Chesapeake Bay impact structure, NASA Langley Research Center, Hampton, Virginia","interactions":[{"subject":{"id":70242740,"text":"pp1688I - 2005 - High-resolution seismic-reflection image of the Chesapeake Bay impact structure, NASA Langley Research Center, Hampton, Virginia","indexId":"pp1688I","publicationYear":"2005","noYear":false,"chapter":"I","title":"High-resolution seismic-reflection image of the Chesapeake Bay impact structure, NASA Langley Research Center, Hampton, Virginia"},"predicate":"IS_PART_OF","object":{"id":69857,"text":"pp1688 - 2005 - Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys","indexId":"pp1688","publicationYear":"2005","noYear":false,"title":"Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys"},"id":1}],"isPartOf":{"id":69857,"text":"pp1688 - 2005 - Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys","indexId":"pp1688","publicationYear":"2005","noYear":false,"title":"Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys"},"lastModifiedDate":"2023-04-14T16:14:13.83648","indexId":"pp1688I","displayToPublicDate":"2005-01-11T11:02:47","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1688","chapter":"I","title":"High-resolution seismic-reflection image of the Chesapeake Bay impact structure, NASA Langley Research Center, Hampton, Virginia","docAbstract":"A 1-kilometer-long (0.62-mile-long) seismic reflection and refraction profile collected at the National Aeronautics and Space Administration (NASA) Langley Research Center, Hampton, Va., provides a detailed image of part of the annular trough of the buried, 35-million-year-old Chesapeake Bay impact structure. This profile passes within 5 meters (m; 16.4 feet (ft)) of a 635.1-m-deep (2,083.8-ft-deep), continuously cored and geophysically logged test hole at the Langley Center (the USGS-NASA Langley corehole). High-resolution seismic reflection images (having a common-depth-point spacing of 2.5 m (8.2 ft)) of the upper 1,000 m (3,281 ft) along the seismic profile were generated by using refraction velocities and corehole sonic velocities to convert from time sections to depth sections.
Time-distance, unmigrated depth-distance, and migrated depth-distance images show lateral variations in the geologic units observed in the USGS-NASA Langley corehole. A high-amplitude reflection at 630 to 625 m (2,067 to 2,051 ft) depth on the migrated depth image correlates with the top of weathered granite (the Langley Granite) at 626.3 m (2,054.7 ft) in the Langley core. Additional high-amplitude reflections below that depth likely represent a weathering profile developed in the upper part of the granite. Diffractions on the unmigrated images suggest that the granite contains numerous inhomogeneities that may consist of mineral veins and mineralized faults and fractures, as seen in the granite cores.
Above the granite, crater unit A (minimally to moderately disturbed sands and clays of the Cretaceous Potomac Formation) is characterized by semicontinuous, horizontal and moderately inclined reflections that are broken by pervasive, subvertical, small-offset faults. Sediments of the lower beds of crater unit A below 558.1 m (1,831.0 ft) in the core have horizontal bedding and are nearly pristine. Above that depth, the upper beds of crater unit A contain thick fluidized sand intervals and fractured clay-silt beds. The contact between the granite and crater unit A is essentially horizontal on the migrated depth profile and shows minor relief produced by a few steeply dipping faults.
Above crater unit A, the lower beds of crater unit B are lithologically similar to the upper beds of crater unit A and display similar impact-generated deformation. In the migrated depth image, crater unit A and the lower beds of crater unit B are combined into one unit. A thin zone (0.3 m (1.0 ft) thick) of injected glauconitic sediment at the base of the lower beds (at 442.5 m (1,451.7 ft) depth) is the only occurrence of exotic material in the lower beds of crater unit B in the core.
The upper beds of crater unit B (above 427.7 m (1,403.3 ft) depth) are represented by discontinuous, locally weak, isolated, or inclined reflections on the migrated depth image. In the core, the upper beds of crater unit B are divided into megablocks and megablock zones that consist of fragmented sediments of the Potomac Formation. The megablocks are separated by matrix zones that consist of smaller blocks of sediments of the Potomac Formation suspended in a matrix of native disaggregated sediments of the Potomac Formation and injected, exotic disaggregated, glauconitic Upper Cretaceous and lower Tertiary marine sediments. Angular relationships and offsets of reflections across the high-relief contact between the upper beds of crater unit B and the underlying combined crater unit A and the lower beds of crater unit B suggest that the contact is a dip-slip fault locally.
Above a contact with crater unit B at a depth of 269.4 m (884.0 ft), the Exmore beds are represented by strong, continuous and discontinuous, overstepping reflections that suggest division of the Exmore into four laterally discontinuous depositional subunits. Two of these subunits are present near the Langley corehole on the seismic images and are recognized in the core (Gohn and others, this volume, chap. C). In the Langley core, the Exmore beds consist of clasts of Cretaceous and Tertiary preimpact sediments and cataclastic, shocked, pre-Mesozoic igneous rocks suspended in a matrix of calcareous, muddy, quartz-glauconite sand and granules that contains shocked quartz.
The dipping, truncated, and disrupted reflections within crater units A and B are interpreted to represent a 550-m-wide (1,805-ft-wide), stratabound collapse structure. This structure does not affect the underlying basement granite or the lower beds of crater unit A, nor does it affect the base of the Exmore beds above crater unit B. The collapse structure is not bounded laterally by major normal faults. Instead, structural displace ments appear to be distributed among abundant short, smalloffset faults and intervals of fluidized sediment. Fluidized sands above 558 m (1,831 ft) depth in crater unit A are interpreted as a low-strength zone that accommodated the widespread, latestage, gravitational collapse of the impact structure. The pro posed Langley collapse structure may be analogous to stratabound grabens in the outer zone of the Silverpit crater (North Sea).
The Exmore beds are interpreted as impact-generated, ocean-resurge deposits. The upper contact of the Exmore section is a wavy, semicontinuous reflection that may represent large bedforms produced by resurge currents or returning impact-generated tsunamis, or it may represent the unmodified blocky or hummocky top of the final Exmore debris flow. Typically continuous, nearly horizontal reflections characterize the upper Eocene to Pleistocene postimpact section of dominantly marine sediments.
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2005 - Paleontology of the upper Eocene to quaternary postimpact section in the USGS-NASA Langley core, Hampton, Virginia","interactions":[{"subject":{"id":70242738,"text":"pp1688H - 2005 - Paleontology of the upper Eocene to quaternary postimpact section in the USGS-NASA Langley core, Hampton, Virginia","indexId":"pp1688H","publicationYear":"2005","noYear":false,"chapter":"H","title":"Paleontology of the upper Eocene to quaternary postimpact section in the USGS-NASA Langley core, Hampton, Virginia"},"predicate":"IS_PART_OF","object":{"id":69857,"text":"pp1688 - 2005 - Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys","indexId":"pp1688","publicationYear":"2005","noYear":false,"title":"Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys"},"id":1}],"isPartOf":{"id":69857,"text":"pp1688 - 2005 - Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys","indexId":"pp1688","publicationYear":"2005","noYear":false,"title":"Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys"},"lastModifiedDate":"2023-04-14T16:00:49.946324","indexId":"pp1688H","displayToPublicDate":"2005-01-11T10:43:56","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1688","chapter":"H","title":"Paleontology of the upper Eocene to quaternary postimpact section in the USGS-NASA Langley core, Hampton, Virginia","docAbstract":"The USGS-NASA Langley corehole was drilled in 2000 in Hampton, Va. The core serves as a benchmark for the study of calcareous nannofossils, dinoflagellates, diatoms and silico flagellates, mollusks, ostracodes, planktonic foraminifera and bolboformids, and vertebrate remains in the upper Eocene, Oligocene, Miocene, and Pliocene sediments in southeastern Virginia. These sediments were deposited after the comet or asteroid impact that produced the Chesapeake Bay impact structure.
The Chickahominy Formation was deposited rapidly in outer neritic to upper bathyal marine environments during the last 2 million years of the late Eocene. The Drummonds Corner beds are newly recognized in the Langley core. These beds appear to represent shallower water or more nearshore deposition than the underlying Chickahominy deposits. Paleontology indicates an age in the later part of the early Oligocene, with a sharp floral and faunal break between the Drummonds Corner beds and the underlying Chickahominy Formation. Late Oligocene sedimentation is represented by the Old Church Formation.
The record of early and middle Miocene deposition in the Langley core is incomplete. The Calvert Formation records brief episodes of deposition in three members, which are separated by unconformities and are called the informal Newport News beds, the Plum Point Member, and the Calvert Beach Member.
A second episode of rapid deposition at the Langley site is preserved as the upper Miocene St. Marys and Eastover Formations. The Eastover is overlain unconformably by the Yorktown Formation, which is both late early and early late Pliocene. The highest unit, the Tabb Formation (Pleistocene), was not studied paleontologically.
Continued movement along faults and fractures of the crater and nearby region may have enhanced the contributions of older material into the various units filling the Chesapeake Bay impact crater, as suggested by the conspicuous reworking of microfossils in many of the samples from the upper Eocene and younger units in the USGS-NASA Langley core.
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","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1688","usgsCitation":"Horton, J., Powars, D.S., and Gohn, G., 2005, Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys (Version 1.0): U.S. Geological Survey Professional Paper 1688, 467 p., https://doi.org/10.3133/pp1688.","productDescription":"467 p.","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":6190,"rank":3,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/2005/1688/ak/","linkFileType":{"id":5,"text":"html"}},{"id":402076,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_75563.htm","linkFileType":{"id":5,"text":"html"}},{"id":90483,"rank":4,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1688/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":121027,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1688/report-thumb.jpg"}],"country":"United States","state":"Virginia","city":"Hampton","otherGeospatial":"Chesapeake Bay impact structure","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.48956298828125,\n 36.87302936279296\n ],\n [\n -75.89630126953125,\n 36.87302936279296\n ],\n [\n -75.89630126953125,\n 37.35924242260126\n ],\n [\n -76.48956298828125,\n 37.35924242260126\n ],\n [\n -76.48956298828125,\n 36.87302936279296\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699e5a","contributors":{"authors":[{"text":"Horton, J. 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The data are primarily from mesic, hilly and mountainous sites ranging from the westernmost tip of the Alaska Peninsula to the northern Kenai Peninsula, spanning 1,000 km on an E–W gradient and 700 km on a N–S gradient. 127 relevés from 18 sites represent the range of structural and compositional variation in the matrix of vegetation and landform diversity. Data were analyzed by multivariate and traditional Braun-Blanquet methods. One association is distinguished, Sambuco racemosi-Alnetum viridis ass. nov. with three new subassociations, oplopanacetosum horridi, typicum, and rubetosum spectabilis with the latter subdivided into four variants. These phytocoena are well-differentiated, although they form a syntaxonomical continuum. The composition and structure of these communities are described and interpreted in relation to complex environmental factors; these are analyzed using Jancey's ranking on F-values. Community composition is primarily related to elevation, longitude, soil moisture, and latitude. Phytogeographic comparison of southwestern Alaska alder communities with those elsewhere in the North Pacific suggests a close floristic relationship to those of southcentral, southeastern Alaska and coastal British Columbia, Canada. All these communities belong to the same association, while those of the eastern and southern parts of the Kamchatka Peninsula, Russia belong to a different association. Syntaxonomy of the 4 major communities is discussed. Within the Northern Hemisphere, vascular plant species of southwestern Alaska alder thickets primarily occur in East Asia and North America, 36 %; while 26 % are circumpolar, and 22 % are restricted to North America. From a latitudinal perspective, the distribution of vascular plant species within these alder thickets peaks in the high-subarctic, low-subarctic, and temperate latitudinal zones, with low representation of arctic species.
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\"}}]}","volume":"35","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ae7657e4b0abf75cf2bf37","contributors":{"authors":[{"text":"Talbot, Stephen S.","contributorId":73266,"corporation":false,"usgs":true,"family":"Talbot","given":"Stephen S.","affiliations":[],"preferred":false,"id":355658,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Talbot, Sandra L. 0000-0002-3312-7214 stalbot@usgs.gov","orcid":"https://orcid.org/0000-0002-3312-7214","contributorId":140512,"corporation":false,"usgs":true,"family":"Talbot","given":"Sandra","email":"stalbot@usgs.gov","middleInitial":"L.","affiliations":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"preferred":true,"id":355657,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Daniels, F. J. A.","contributorId":96196,"corporation":false,"usgs":true,"family":"Daniels","given":"F.","email":"","middleInitial":"J. A.","affiliations":[],"preferred":false,"id":355659,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70160107,"text":"70160107 - 2005 - Forestry practices and aquatic biodiversity: Fish","interactions":[],"lastModifiedDate":"2015-12-14T09:46:43","indexId":"70160107","displayToPublicDate":"2005-01-01T12:30:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":3,"text":"Organization Series"},"seriesTitle":{"id":221,"text":"Technical Bulletin","active":false,"publicationSubtype":{"id":3}},"seriesNumber":"908","title":"Forestry practices and aquatic biodiversity: Fish","docAbstract":"
In the Pacific Northwest, fish communities are found in a diverse array of aquatic habitats ranging from the large coastal rivers of the temperate rainforests, to the fragmented and sometimes ephemeral streams of the xeric interior basins, and high-elevation streams and lakes in the mountainous areas (Rieman et al. 2003). Only high-elevation lakes and streams isolated above barriers to fish passage remained historically devoid of fish because they were never invaded following Pleistocene glaciation (Smith 1981). Despite this widespread distribution and once great population abundances, taxonomic diversity of fishes in these forested systems is naturally lower than in aquatic habitats in the eastern U.S. (Reeves, Bisson, and Dambacher 1998).
Interactions among factors that influence species richness in aquatic systems (e.g., basin size, long-term stability of habitat, and barriers to colonization; Smith 1981) continue to influence the occurrence and persistence of fishes in these systems today. Consequently, the larger low-elevation rivers and estuaries support the greatest variety of fish species. In the high-elevation tributary streams, fish communities are less complex because these aquatic systems were less climatically and geologically stable, and fish populations were smaller and more prone to local extirpation. Furthermore, barriers to fish passage inhibited dispersal and colonization (Smith 1981). Streams in forested landscapes generally support salmon and trout, Oncorhynchus spp., whitefish Prosopium spp., sculpins Cottus spp., suckers Catostomus spp., and minnows (Cyprinidae), but in some of the colder streams, chars (e.g., Salvelinus confluentus and Salvelinus malma) and lampreys (Petromyzontidae)may also occur (Rieman et al. 2003).
Although biodiversity defined in terms of fish species richness is low in the Pacific Northwest, intraspecific variability is high, and polytypic fish species are common in the diverse aquatic habitats of the region. For example, the salmonids in the coastal rivers and streams, and the larger interconnected streams, rivers, and lakes of the interior exhibit a variety of ecotypes and migratory life histories (Healey 1986; Trotter 1989; Larson and McIntire 1993; Northcote 1997). This life-history variation appears to be associated with adaptation to spatial and temporal variation in environment (e.g., Schaffer and Elson 1975; Carl and Healey 1984; Beacham and Murray 1987), and there is some evidence of the genetic heritability of life-history traits (Carl and Healey 1984; Gharrett and Smoker 1993; Hankin, Nicholas, and Downey 1993). Persistence of any level of biological organization (e.g., life-history type, population, metapopulation, subspecies, species, community) is related to the interaction of environmental and biological components, and intraspecific diversity is a means of spreading risk (sensu den Boer 1968) of extirpation in dynamic environments (Gresswell 1999).
Unfortunately, despite the broad distribution and extensive intraspecific diversity, persistence of native fishes is uncertain in the Pacific Northwest. Many populations of anadromous salmonids, once synonymous with vigorous biological communities throughout the region, are threatened with extinction (Nehlsen, Williams, and Lichatowich 1991; Frissell 1993; Thurow, Lee, and Rieman 1997). Furthermore, over half of the native taxa in the Columbia River Basin are either listed under the Endangered Species Act, are being considered for listing, or are deemed sensitive by the management agencies (Lee et al. 1997; Thurow, Lee, and Rieman 1997). Potamodromous species like bull trout Salvelinus confluentus are estimated to occur as strong populations in less than 5% of their potential range (Rieman, Lee, and Thurow 1997). Although not currently listed under the endangered species list, the coastal cutthroat trout Oncorhynchus clarki is managed as a sensitive species in Oregon and California (Hall, Bisson, and Gresswell 1997). Native non-game fishes have rarely been monitored, but populations of species such as large-scale suckers (Catostomus macrocheilus), squawfish (Ptychocheilus umpquae), and Pacific lamprey (Lampetra tridentata) also are declining in some drainages (Oregon Department of Fish and Wildlife, unpublished data).